Hydroclimatic Variability in the Panama Bight Region During Termination 1 and the Holocene - Integrated Analysis of Interglacial Climate Dynamics (INTERDYNAMIC) - page 61

Fig. 1 a Locations of sediment cores collected during Knorr Cruise KNR176-2, which were
analyzed. Cores used in previous studies (Benway et al. 2006 ; Leduc et al. 2007 ) are also shown.
The location of the Rio San Juan delta is marked by an arrow. The H1 anomalous SSS or rainfall
dipole is schematically illustrated by blue (wet) and red (dry) shading. b From bottom to top:
leading principal component of 44GGC/46JPC, 36JPC, and 32JPC alkenone SST records; sea-
level corrected δ

18

O seawater records of 36JPC and 44GGC/46JPC; difference between the two

18 14

O seawater records. Grey triangles mark AMS C dates for core 32JPC, calibrated using

δ

Calib5.0.1-Marine04 without local offset

A modern control run shows that the model is able to successfully simulate the
annual cycle of the regional wind pattern including strong northeast trades in late
winter and early spring, and a large transport of water vapor from the Paci cto

western Colombia with the Choco Jet during summer (not shown).
Freshwater hosing experiments under different background climatic conditions
(pre-industrial, 8.5 thousand years (ka) before present (BP) early Holocene, and
Last Glacial Maximum) were carried out to identify possible feedbacks between
AMOC strength and tropical atmospheric vapor transports, with a particular eye
towards the (early Holocene experiment) and H1 (glacial

experiment). In these hosing experiments, freshwater at a rate of 0.2 Sv is injected
into the northern North Atlantic for 400 years leading to substantial weakening of
the AMOC.

“ 8.2 ka BP event ”